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Carbon Isotope Chemostratigraphy and Sea Geological Magazine Carbon isotope chemostratigraphy and sea- www.cambridge.org/geo level history of the Hirnantian Stage (uppermost Ordovician) in the Oslo–Asker district, Norway 1 † 2,3 Original Article Mikael Calner , Johan Fredrik Bockelie , Christian M.Ø. Rasmussen , Hanna Calner1, Oliver Lehnert4 and Michael M. Joachimski4 Cite this article: Calner M, Bockelie JF, Rasmussen CMØ, Calner H, Lehnert O, and 1Department of Geology, Lund University, Sölvegatan 12, SE-223 62 Lund, Sweden; 2Natural History Museum of Joachimski MM. Carbon isotope – 3 chemostratigraphy and sea-level history of the Denmark, University of Denmark, Øster Voldgade 5 7, DK-1350, Copenhagen, Denmark; GLOBE Institute, 4 Hirnantian Stage (uppermost Ordovician) in the University of Copenhagen, Copenhagen, Denmark and GeoZentrum Nordbayern, Friedrich-Alexander University Oslo–Asker district, Norway. Geological Erlangen-Nürnberg (FAU), Schlossgarten 5, D-91054, Erlangen, Germany Magazine https://doi.org/10.1017/ S0016756821000546 Abstract δ13 Received: 10 August 2020 We present a Ccarb chemostratigraphy for the Late Ordovician Hirnantian Stage based on Revised: 4 May 2021 208 whole-rock samples from six outcrops in the Oslo–Asker district, southern Norway. Our Accepted: 21 May 2021 data include the Norwegian type section for the Hirnantian Stage and Ordovician–Silurian Keywords: boundary at Hovedøya Island. The most complete record of the Hirnantian Isotope Carbon HICE; oolite; incised valley; glaciation; Excursion (HICE) is identified in a coastal exposure at Konglungø locality where the preserved brachiopods; Konglungø; Hovedøya part of the anomaly spans a c. 24 m thick, mixed carbonate–siliciclastic succession belonging to δ13 the upper Husbergøya, Langåra and Langøyene formations and where Ccarb peak values Author for correspondence: Mikael Calner, þ ‰ Email: [email protected] reach c. 6 . Almost the entire HICE occurs above beds containing the Hirnantia Fauna, suggesting a latest Hirnantian age for the peak of the excursion. The temporal development †J.F.B. passed away 7 October 2016. of the HICE in southern Norway is associated with substantial shallowing of depositional envi- ronments. Sedimentary facies and erosional unconformities suggest four inferably fourth-order glacio-eustatically controlled sea-level lowstands with successively increased exposure and ero- sion to the succession. The youngest erosional unconformity is related to the development of incised valleys and resulted in cut-out of at least the falling limb of the HICE throughout most of the Oslo–Asker district. The fill of the valleys contains the falling limb of the HICE, and the postglacial transgression therefore can be assigned to the latest part of the Hirnantian Age. We address the recent findings of the chitinozoan Belonechitina gamachiana in the study area and its relationship to the first occurrence of Hirnantia Fauna in the studied sections, challeng- ing identification of the base of the Hirnantian Stage. 1. Introduction The Hirnantian Age in the latest Ordovician is of wide international interest due to its associ- ation with the peak of the early Palaeozoic Icehouse (EPI; Page et al. 2007), the Late Ordovician Mass Extinction (LOME; Finnegan et al. 2012; Harper et al. 2014; Ling et al. 2019; Rasmussen et al. 2019; Wang et al. 2019) and an associated major anomaly to the global carbon cycle, the Hirnantian Isotope Carbon Excursion (HICE; Brenchley et al. 2003; Kaljo et al. 2008; Bergström et al. 2013; Subías et al. 2015; Mauviel & Desrochers, 2016). The possibility of assessing the Hirnantian Stage and demonstrating the precise interrelationship of stage boundaries, biostra- tigraphy, sea-level trends and the temporal development of the HICE is hampered by the global rarity of complete sections: the HICE is to date recorded from several tens of localities world- wide, but few, if any, of the associated outcrops or core sections have a continuous sedimentary record due to the contemporaneous glacio-eustasy (e.g. Loi et al. 2010; Ghienne et al. 2014). Formally, the base of the Hirnantian is defined as the First Appearance Datum (FAD) of the graptolite Metabolograptus extraordinarius 0.39 m below the Kuanyinchiao Bed in the Wangjiawan North Section, Hubei province, China (Chen et al. 2006; Gorjan et al. 2012). © The Author(s), 2021. Published by Cambridge At the immediately adjacent Wangjiawan Riverside Section, the HICE starts very close to University Press. This is an Open Access article, the FAD of M. extraordinarius (Gorjan et al. 2012). Recent U–Pb dates from a continuous sec- distributed under the terms of the Creative tion at Wanhe in southwest China suggest that the duration of the entire Hirnantian Age is as Commons Attribution licence (http:// creativecommons.org/licenses/by/4.0/), which little as 0.47 ± 0.34 Ma, and thus considerably shorter than previously understood (Ling et al. permits unrestricted re-use, distribution and 2019). Bergström et al. (2009) subdivided the Hirnantian Stage into two stage slices, named Hi1 reproduction, provided the original article is and Hi2. Hi1 is defined as strata between the base of the Metabolograptus extraordinarius properly cited. Graptolite Zone and the end of HICE. Hi2 is thus defined as strata between the end of the HICE and the base of the Akidograptus ascensus Graptolite Zone, marking the top of the Ordovician. In Baltoscandia the HICE has been particularly studied from sections in the East Baltic area (Kaljo et al. 2001, 2004a, 2007, 2008, 2012; Ainsaar et al. 2004, 2010; Meidla et al. 2004; Hints Downloaded from https://www.cambridge.org/core. IP address: 170.106.33.14, on 24 Sep 2021 at 23:35:19, subject to the Cambridge Core terms of use, available at https://www.cambridge.org/core/terms. https://doi.org/10.1017/S0016756821000546 2 M Calner et al. et al. 2010, 2014; Bauert et al. 2014; Ainsaar, 2015). Important data unconformity below the Silurian deposits. Brenchley & have also emerged from Sweden (Schmitz & Bergström, 2007; Newall (1975) studied the sedimentology and palaeontology Bergström et al. 2012, 2013; Ebbestad et al. 2015) where the pre- of the Katian through Hirnantian and produced palaeogeo- served Hirnantian Stage is normally only a few metres thick and graphical maps for the upper Fjord area. They showed that associated with marked disconformities (e.g. Bergström et al. the facies pattern in Oslo–Asker was complex, with an ‘eastern’ 2012, 2013). and ‘western’ facies subdivision; the western parts being richer δ13 This study aims to establish a Ccarb chemostratigraphy in carbonates whereas siliciclastics are more important in the for the Hirnantian Stage of the Oslo–Asker district of eastern part. Johnson & Baarli (2018) further elaborated on this Norway. This region represents the margin of Baltoscandia subdivision and showed that, in the late Hirnantian, higher land and faced the closing Iapetus Ocean towards the west during areas existed in the northwest, whereas marginal marine areas theearlystagesoftheCaledonianOrogeny.Wepresentδ13C were found to the southeast, and that incised valleys were situ- data from six outcrops (Fig. 1;Appendix1), including from ated between these areas. The stratigraphic interfingering of the the Norwegian type section for the Hirnantian Stage and the ‘eastern’ and ‘western’ facies is obvious in central positions Ordovician–Silurian boundary at Hovedøya Island and from where distinct lithostratigraphic units therefore are recurrently an incised valley fill that represents the ‘missing strata’ at a occurring in a stratigraphic section; this is exemplified in the major unconformity resulting from Hirnantian glacio-eustasy present study. (Bockelie et al. 2017). Our primary goal has been to identify the A recent paper by Bockelie et al.(2017) presents a historic back- HICE in order to understand the degree of preservation of ground to the successive improvements in understanding that have Hirnantian strata, and thus illustrate the stratigraphic com- taken place with regard to the Ordovician–Silurian boundary inter- pleteness of the exposed successions in the area. This is par- val in the area, and also provides a detailed description and partial ticularly warranted as Norway is largely a white spot on the revision of the stratigraphy of these rocks. Their revised stratigra- map in terms of Ordovician carbon isotope stratigraphy. phy is followed in the present paper (Fig. 2). Bergström et al. (2010) documented the Katian Guttenberg Carbon Isotope Excursion (GICE) from the Nes-Hamar dis- trict north of Oslo. Apart from this, only a few previous studies 3. Material and methods have shown a partial record of the upper Katian and/or Hirnantian stages from localities in the Oslo–Asker district For this paper we have studied and sampled five formations span- (Brenchley et al. 1997; Brenchley & Marshall, 1999; Kaljo ning the upper Katian through lowermost Silurian of the Oslo– et al. 2004b; Bergström et al. 2006;Amberget al. 2017). Asker district: the Skogerholmen Formation, the Husbergøya Shale Formation, the Langåra Limestone–Shale Formation, the Langøyene Sandstone Formation and the Solvik Formation 2. Geological setting and stratigraphy (Fig. 2). M.C. and H.C. studied natural outcrops at six locations At the end of the Ordovician period, present-day southern Norway during field seasons 2014–16, and J.F.B. participated in two of these was situated near latitude 30°S (Scotese & McKerrow, 1991; fieldworks. The studied localities include the southwestern shore of Torsvik & Cocks, 2013). The Ordovician rocks exposed in and the island Hovedøya (59° 53 0 30.01″ N, 10° 43 0 52.43″ E), Pilbogen around Oslo city and in the many islands in the upper Oslo Bay in western Brønnøya (base of section at 59° 51 0 10.90″ N, 10° Fjord area form part of a fault-controlled graben with a c. 31 0 34.28″ E; top of section at 59°51 0 11.32″ N, 10° 31 0 33.95″ E), 2500 m thick lower Palaeozoic succession (Bruton & Williams, Store Ostsundet, more specifically near the intersection of 1982; Nakrem & Rasmussen, 2013). The Ordovician part of this Vierndroget and Viernveien in eastern Brønnøya (59° 51 0 succession is c.
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